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Article

Petrogenesis and Tectonic Implication of the Hongtaiping High-Mg Diorite in the Wangqing Area, NE China: Constraints from Geochronology, Geochemistry and Hf Isotopes

by
Siyu Lu
1,
Yunsheng Ren
1,2,*,
Qun Yang
1,
Yujie Hao
1,3 and
Xuan Zhao
4
1
College of Earth Sciences, Jilin University, Changchun 130061, China
2
Institute of Disaster Prevention, Langfang 065201, China
3
Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, Changchun 130026, China
4
Jiangxi Earthquake Agency, Nanchang 330026, China
*
Author to whom correspondence should be addressed.
Minerals 2022, 12(8), 1002; https://doi.org/10.3390/min12081002
Submission received: 27 June 2022 / Revised: 26 July 2022 / Accepted: 3 August 2022 / Published: 8 August 2022
(This article belongs to the Special Issue Composition, Geochronology and Geodynamic Implications of Igneous Rock)
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Abstract

:
This study presents new data from zircon U–Pb dating and Hf isotope analysis, as well as whole-rock major- and trace-element compositions of the Hongtaiping high-Mg diorite in the Wangqing area of Yanbian, NE China. Laser ablation inductively coupled plasma mass spectrometry (LA–ICP–MS) zircon U–Pb dating gives an eruption age of ca. 267 Ma for the high-Mg diorite. These samples have MgO contents of 13.30% to 16.58% and high transition metal element concentrations, classified as sanukite. Their rare earth element (REE) contents range from 45.2 to 68.4 ppm and are characterized by slightly positive Eu anomalies (Eu/Eu* = 1.08–1.17). They show enrichment in light REEs (LREEs) and depletion in heavy REEs (HREEs), with LREE/HREE ratios = 6.54–6.97 and (La/Yb)N values = 7.24–8.08. The Hongtaiping high-Mg diorite is enriched in Rb, U, K, and Sr, but depleted in Th, Nb, and Ta. High MgO contents, Mg# values, and transition metal element concentrations imply that the magma experienced insignificant crystallization fractionation and crustal contamination. Relatively homogenous positive Hf isotopic values indicate that the original magma was generated by the partial melting of a depleted mantle wedge that was metasomatized by subducting slab fluids. The magma was generated by the moderate degree partial melting (20%–30%) of a garnet lherzolite source. Combined with previous studies, this shows that the high-Mg diorite was formed by the northward subduction of the Paleo-Asian oceanic plate during the Middle Permian.

1. Introduction

As an important method for studying the time limitation of plate subduction, the tectonic setting of the subduction zone, and the tectonic evolution of the orogenic belt, high-magnesium andesite (HMA) is one of the hotspots of geoscience research [1,2,3,4,5,6,7,8]. HMA refers to those andesites characterized by higher MgO, lower TFeO/MgO, Al2O3, and CaO contents than typical island arc andesite [8]. Presently, it is divided into four main types: boninite, bajaite, adakitic HMA, and sanukite. Boninite is a volcanic rock that has a high magnesium content and is rich in fluid and saturated with silica [9,10]. High SiO2 (>52%) and MgO (>8%) contents, and low TiO2 (<0.5%) contents, are its key geochemical characteristics [11]. Bajaite is a suite of magnesian andesite and basalt, and basaltic andesite [4,5], which is characterized by high Sr (506–3800 ppm) and Ba (280–2300 ppm) concentrations, and high Sr/Y ratios [7]. Adakitic HMA has higher MgO, Mg#, Cr, and Ni concentrations than adakite. Sanukite has the characteristics of a high MgO content, high Cr and Ni concentrations, and enrichment in large-ion lithophile elements (LILEs) [6]. Sanukite includes intrusive and volcanic rocks with the above sanukitic geochemical features [12].
Presently, several issues in NE China, especially the final closure time of the Paleo-Asian Ocean, are in debate. Most researchers suggest that the final closure happened between the Late Permian and Middle Triassic [13,14,15,16,17,18,19], but other researchers proposed that the Paleo-Asian Ocean closed during the Late Devonian and Early Carboniferous [20,21,22]. The Yanbian area, located in the eastern segment of the Central Asian Orogenic Belt (CAOB), experienced the superimposition and transformation of the Paleo-Asian Ocean and Paleo-Pacific Ocean domains, which resulted in multiple periods of magmatic and metallogenic events [23,24], as well as ideal conditions to solve these controversies. Previous studies mainly focused on the geochronology, geochemistry, and source area of felsic igneous rocks in this region [14,17,18,25,26,27,28,29,30]. Due to lesser exposure, relevant work on mafic rocks concentrated on the Wudaogou complex [31,32] and Qianshan intrusion [33,34,35]. Until now, only Li et al. [26] discovered high-Mg diorite in the Hunchun area and proposed that these rocks likely formed in the Middle Triassic from mantle peridotite by reacting with Si-rich melts, similar to the magmatic processes of sanukite. Thus, the data on high-Mg diorite presented in this paper can create diagnostic constraints for the tectonic evolution of the eastern Paleo-Asian Ocean.
This study presents new data on LA–ICP–MS zircon U–Pb dating, in situ Hf isotopic analysis, and whole-rock major- and trace-element analysis. Some key issues are discussed, including the emplacement age, petrogenesis, and tectonic setting of the high-Mg diorite. The data and discussions provide new evidence for the tectonic evolution of the Yanbian area.

2. Geological Setting and Sample Descriptions

The CAOB (Figure 1a) is one of the largest and most complex orogens in the world [36,37,38,39]. The eastern segment of the CAOB (accepted as the Xing’an–Mongolia Orogenic Belt, XMOB) is composed of a series of microblocks and orogens consisting of Phanerozoic island arc and accretionary/collisional complex, and it experienced the reformation of the Paleo-Asian Ocean, the Mongo-Okhotsk Ocean, and the Paleo-Pacific Ocean regimes during the Paleozoic to Mesozoic [13,15,16,17,19,38,39,40,41,42]. Microblocks mainly consist of, from northwest to southeast, the Erguna, Xing’an, Songnen-Zhangguangcai Range, Jiamusi, and Khanka massifs (Figure 1b). Orogens include the Duobaoshan island arc belt and the continental margin accretionary belt of the NCC [16,43]. The Yuejinshan Complex and Nadanhada Terrane to the east of the Jiamusi Massif developed during the Permian and Mesozoic [44,45].
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Figure 1. (a) Simplified tectonic map showing the location of the CAOB (modified from [36]); (b) tectonic divisions of NE China (modified from [43]); (c) simplified regional geologic map of the Yanbian area (modified from [35]).
Figure 1. (a) Simplified tectonic map showing the location of the CAOB (modified from [36]); (b) tectonic divisions of NE China (modified from [43]); (c) simplified regional geologic map of the Yanbian area (modified from [35]).
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The Yanbian area of NE China, bounded by the Dunhua–Mishan Fault to the northwest and the Gudonghe–Fuerhe Fault to the south [14,35,46], is located among the continental margin accretionary belt, Songnen–Zhangguangcai Range, and Jiamusi and Khanka massifs. Archean to early Proterozoic greenschist and amphibolite–facies metamorphic rocks are only distributed in the Helong area [14,35,46,47]. Paleozoic strata experiencing various degrees of metamorphism and deformation and Mesozoic–Cenozoic volcanics and sediments develop widely [13]. The voluminous Phanerozoic granitoids that make up the Yanbian area known as the “granite ocean” are associated with limited and scattered mafic intrusions (Figure 1c; Table 1), and constitute the magmatic rocks of this area. As found in a previous study, there were four periods of magmatism, namely the late Permian to Early Triassic (280–245 Ma), the Late Triassic (225–220 Ma), the Jurassic (200–150 Ma), and the Early Cretaceous (135–105 Ma) [23,48].
The Hongtaiping Cu polymetallic deposit, with a proven reserve of 6257 t Cu, 2472 t Pb, and 13,527 t Zn, is located in Wangqing County of the Yanbian area. Strata in the ore district are mainly composed of the Middle Permian Miaoling Formation felsic volcanic rocks, and sedimentary rocks with limestone intercalations [24,48]. Triassic and Jurassic felsic dikes were documented. Two mineralization types are identified at the Hongtaiping deposit, i.e., stratiform VMS-type mineralization (268.3 ± 2.6 Ma) [24] in the Miaoling Formation and quartz-sulfide vein-type mineralization (206.8 ± 9.0 Ma) [49] controlled by fractures.
Table
Table 1. Permian and Early Triassic mafic intrusions in the Yanbian area.
Table 1. Permian and Early Triassic mafic intrusions in the Yanbian area.
OrderSampleLatitudeLongitudePlutonLithologyAge (Ma)MethodReference
1JXNC-I-2 WugaogouGabbro270 ± 10SHRIMP[31]
2YH8-1 QianshanGabbro282 ± 2LA–ICP–MS[34]
3JXB-6A WudaogouGabbroic diorite263.5 ± 5.1LA–ICP–MS[32]
406HCH-5542°58′08″130°55′25″QianshanGabbro273 ± 2SHRIMP[33,35]
509HC-1843°01′11″130°58′25″ShuguangDiorite257 ± 2SHRIMP[35]
609HC-2643°40′11″129°55′30″WangqingDiorite263 ± 3LA–ICP–MS[35]
709HC-1243°01′09″130°19′25″QinggoushanGabbro254 ± 3LA–ICP–MS[38]
8HC0143.0148417°131.000115° Gabbro266.9 ± 5.2LA–ICP–MS[50]
9B411742°39′35″129°29′57″ZhixinHornblende gabbro251 ± 1LA–ICP–MS[51]
1017HTP-643°34′19″129°33′21″HongtaipingHigh-Mg diorite267.0 ± 1LA–ICP–MSThis study
Sample 17HTP-6, a high-Mg diorite (Figure 2a), was collected from the open pit of the Hongtaiping deposit (43°34′19″ N, 129°33′21″ E) for LA–ICP–MS zircon U–Pb dating and in situ Hf isotopic and whole-rock chemical analysis. The high-Mg diorite is grayish-white and displays an idiomorphic–hypidiomorphic granular texture and massive structure (Figure 2a). It consists of hornblende (~55%), plagioclase (~40%), and minor alkali feldspar and quartz (~5%) (Figure 2b,c).

3. Analytical Methods

3.1. Zircon U–Pb Geochronology

Zircon grains were separated through a combination of magnetic and heavy liquid separation techniques and were handpicked under a binocular microscope at the Beijing Geoanalysis Co., Ltd. (Beijing, China). The handpicked zircons were mounted in epoxy resin and polished to about half their thickness. All zircon grains were photographed in transmitted and reflected light, as well as imaged with cathodoluminescence (CL).
LA–ICP–MS zircon U–Pb dating was carried out at the Key Laboratory of Mineral Resources Evaluation in Northeast Asia, Ministry of Natural Resources, Jilin University, Changchun, China, using an Agilent 7500a inductively coupled plasma mass spectrometer (ICP-MS) equipped with a 193-nm ArF Excimer laser system (LA). The standard zircon, 91500 [52], was used as an external standard to normalize isotopic fractionation during analysis. The analytical details were described by Hao et al. [53].

3.2. Whole-Rock Major and Trace Element Analysis

Five samples were collected for whole-rock chemical analysis. The fresh and unaltered samples were crushed, cleaned with deionized water, and ground to a 200 mesh using an agate mill. Major and trace element analyses were performed at the State Key Laboratory of Ore Deposit Geochemistry, Institute of Geochemistry, Chinese Academy of Sciences (IGCAS), Guiyang, China, using Thermo Fisher ARL Perform’ X 4200 X-ray fluorescence spectrometer (XRF) and PlasmaQuant MS Elite ICP–MS, respectively. The analytical details were described by Qi and Zhou [54]. The analytical results for the major elements had a precision of <5%, as determined using GSR-1 and GSR-3 Chinese national standards, and a precision of <10% for the trace elements using international OU-6 and GBPG-1 standards. The detection limit for the trace element is better than 0.5 ppb, and triplicate analyses were reproducible within 5% for all the elements.

3.3. In Situ Zircon Hf Isotope Analysis

In situ zircon Hf isotope analysis was conducted on the same zircon grains previously subjected to U–Pb isotopic analyses, using a Thermo Neptune-Plus multicollector (MC–ICP–MS) equipped with a Geolas Pro 193-nm ArF excimer laser ablation (LA) system at the Beijing Geoanalysis Co., Ltd. All data were acquired on zircon in single-spot ablation mode with a spot size of 44 μm. The standard zircon GJ-1 [55] was used as a reference material. The detailed analytical procedures were described by Wu et al. [56]. The present-day chondritic ratios of 176Hf/177Hf = 0.282772 and 176Lu/177Hf = 0.0332 [57] were adopted to calculate the εHf(t) values. Hf model ages were calculated as described in Nowell et al. [58], Amelin et al. [59], and Griffin et al. [60].

4. Results

4.1. Internal Structure and Texture of Zircon

The CL images of representative zircons are presented in Figure 3. Zircons mainly have a length of 40–80 μm and a width of 30–60 μm, with aspect ratios of 1:1–2:1. The rims comprise thin overgrowths, are CL-dark, and exhibit faint, poorly developed oscillatory zoning. The core domains are relatively large and bright, and seldom have microfractures or cracks but have abundant micro-inclusions [61].

4.2. Zircon U–Pb Dating

The LA–ICP–MS zircon U–Pb dating results of sample 17HTP-6 are presented in Table 2, and zircon U–Pb concordia diagrams are shown in Figure 4. Fourteen analytical spots produced 206Pb/238U ages of 276–261 Ma (Figure 4a) and yielded a weighted mean 206Pb/238U age of 267.0 ± 2.8 Ma (MSWD = 1.7, n = 14, Figure 4b). Two older ages (405 Ma and 315 Ma) are interpreted to be the crystallization ages of inherited or captured zircons entrained by the magma.

4.3. Major and Trace Element Compositions

Whole-rock major- and trace-element compositions are listed in Table 3. The Hongtaiping high-Mg diorite samples contained SiO2 = 43.96%–46.57%, Al2O3 = 13.34%–14.72%, total Fe2O3 = 10.05%–11.37%, MgO = 13.30%–16.58%, and (Na2O + K2O) = 1.80%–3.22%. The samples contained rare earth elements (REEs) = 45.2–68.4 ppm and were characterized by slightly positive Eu anomalies (Eu/Eu* = 1.08–1.17; Figure 5a). They show enrichment of light REEs (LREEs) and depletion of heavy REEs (HREEs), with LREE/HREE ratios = 6.54–6.97, and (La/Yb)N values = 7.24–8.08. On the primitive mantle (PM)-normalized trace element diagram (Figure 5b), these samples are enriched in Rb, U, K, and Sr and depleted in Th, Nb, and Ta. The high-Mg diorite samples are classified as andesite and basalt series on a Zr/TiO2*0.0001 vs. Nb/Y diagram (Figure 6a) and as calc-alkaline series on a Th vs. Co diagram (Figure 6b).
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Figure 5. (a) Chondrite-normalized REE diagrams; (b) PM-normalized trace element diagrams for the high-Mg diorite. The C1 chondrite-normalized, PM-normalized, OIB, E-MORB, and N-MORB values are from [62]. The IAB values are from [63].
Figure 5. (a) Chondrite-normalized REE diagrams; (b) PM-normalized trace element diagrams for the high-Mg diorite. The C1 chondrite-normalized, PM-normalized, OIB, E-MORB, and N-MORB values are from [62]. The IAB values are from [63].
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Figure 6. (a) Zr/TiO2*0.0001 vs. Nb/Y diagram (modified from [64]); (b) Th vs. Co diagram (modified from [65]).
Figure 6. (a) Zr/TiO2*0.0001 vs. Nb/Y diagram (modified from [64]); (b) Th vs. Co diagram (modified from [65]).
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4.4. In Situ Zircon Hf Isotopic Compositions

In situ zircon Hf isotopic compositions are listed in Table 4. Zircon grains in the high-Mg diorite have initial 176Hf/177Hf ratios of 0.282764–0.282950, with εHf(t) values and TDM2 ages ranging from 6.7 to 12.2 (Figure 7) and 929 to 511 Ma, respectively.
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Figure 7. (a) εHf(t) vs. t(Ma) diagram for zircons from the high-Mg diorite. Xing-Meng = XMOB; YFTB = Yanshan Fold and Thrust Belt (Ranges of XMOB and YFTB are from Yang et al. [66]); (b) detailed distribution of samples in εHf(t) vs. T(Ma) diagram enlarged from the square area in (a). The isotopic data are from [34,35,51].
Figure 7. (a) εHf(t) vs. t(Ma) diagram for zircons from the high-Mg diorite. Xing-Meng = XMOB; YFTB = Yanshan Fold and Thrust Belt (Ranges of XMOB and YFTB are from Yang et al. [66]); (b) detailed distribution of samples in εHf(t) vs. T(Ma) diagram enlarged from the square area in (a). The isotopic data are from [34,35,51].
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5. Discussion

5.1. Emplacement Age of the High-Mg Diorite and Middle Permian Magmatic Event in the Yanbian Area

In this study, zircon grains from the Hongtaiping high-Mg diorite exhibit typical oscillatory growth zoning, with high Th/U ratios (0.47–1.49), indicating their igneous origin [67,68]. The weighted mean 206Pb/238U age of 267.0 ± 2.8 Ma (n = 14) shows that this mafic intrusion emplaced in the Middle Permian. In the Yanbian area, as a result of the continuous subduction of the Paleo-Asian Ocean, the Permian was a notable magmatic activities period [14,17]. Previous studies have proved that the Early and Late Permian are two major stages of magmatism [14,17,18,25,26,34,35,69], whereas a large amount of Middle Permian has been reported. Lithologically, these are dominated by intermediate-felsic compositions with minor mafic intrusions. From east to west in the Yanbian area, the quartz diorite and granodiorite from the Wudaogou Group and gabbro in the Hunchun area have a formation age of 270 to 263 Ma [31,32,70]. Wu et al. [17] and Hou et al. [29] reported Hongshitun monzogranite (266 Ma) and two pyroclastic rocks (271–268 Ma) in the Wangqing area. A series of diorite–granodiorite (271–262 Ma) in the Tianbaoshan ore district has been identified by Ju [71], Sun et al. [72], Yang et al. [73,74], and Zhang et al. [75]. Liukesong gabbro (262 Ma) and granodiorite (263 Ma), and Xiaobutun quartz diorite (260 Ma) in the Dunhua area, have been reported by Liu et al. [27] and Wu et al. [17]. Moreover, Tang et al. [30] reported the monzogranite (265 Ma) in the Helong area in the southern Yanbian. Combined with these dating results, it has been suggested that the Middle Permian was also an important magmatism period in the Yanbian area.

5.2. Petrogenesis of the High-Mg Diorite

5.2.1. Alteration Effects

The Hongtaiping high-Mg diorite samples exhibit relatively high LOI values (4.04%–5.14%). The effects of alteration must be determined before their petrogenesis can be considered. High field-strength elements (HFSEs: e.g., Zr, Y, Nb, Th, and Ti) and transition elements (e.g., Cr, Ni, and Sc) are generally immobile during alteration and weathering [76]. Therefore, only immobile elements were used for the investigation of petrogenesis and tectonic setting of the high-Mg diorite.

5.2.2. Fraction Crystallization

Limited variations of geochemical compositions and high MgO contents, Mg# values, and transition metal element concentrations suggest that the high-Mg diorite resulted from a very low-degree fractional magma [77]. The positive correlations between MgO and Fe2O3t suggest that ferromagnesian minerals such as olivine and clinopyroxene are major fractionating phases [35], whereas the negative correlations between MgO and SiO2, Al2O3, CaO, Na2O, K2O, P2O5, and TiO2 (Figure 8) demonstrate that Ti-bearing minerals, apatite, and plagioclase are not major fractional phases.

5.2.3. Crustal Contamination

Mantle-derived magma experiences crustal contamination during ascent [78]. Negative Nb–Ta anomalies indicate that the magma experienced crustal contamination. However, no significantly positive Zr–Hf anomalies exist, indicating that crustal contamination is not a major mechanism. Lu/Yb (0.15) and Nb/Ta (16.74–17.71) ratios are consistent with mantle-derived magmas (0.14–0.15 and 17.8, respectively) [60], rather than crustal-derived magmas (0.16–0.18 and 11.4, respectively) [79,80]. Low SiO2 contents and high MgO contents, Mg# values, and transition metal element concentrations, combined with homogeneous positive Hf isotopic values, imply that crustal contamination could not play a significant role during the magmatic evolution.

5.2.4. Nature of the Mantle Source

The high-Mg diorite samples in this study have lower SiO2 (43.96%–46.57%) and higher TiO2 contents (0.90%–1.04%) than boninite, lower SiO2 content and Sr concentrations (366–542 ppm) than adakitic HMA, and lower Sr and Ba (66.1–182 ppm) concentrations than bajaite. Due to the relative enrichment in LREEs and LILEs, and the depletion of HREEs, Mg# = 72%–74%, MgO content = 13.30%–16.58%, and Cr and Ni concentrations = 916–1326 ppm and 351–562 ppm, these samples fall into the sanukite area on the classification diagram of HMA (Figure 9a,b). Such geochemical features are distinctly different from crustal-derived rocks [79], together with relatively homogenous positive Hf isotopic values (6.7–12.2), indicating that the primary magma could be derived from the depleted mantle. Their high La/Nb (4.13–4.39) and La/Ta (71.58–76.32) ratios indicate that they were sourced from the lithospheric mantle (La/Nb > 1, La/Ta > 20) rather than the asthenospheric mantle (La/Nb < 1, La/Ta ≈ 10) [81,82]. Negative Nb–Ta anomalies could also be caused by subduction-related fluid or melt metasomatism. The high-Mg diorite showed enrichment in LILEs and LREEs, and depletion in HFSEs and HREEs, consistent with rocks formed in subduction zones [83]. Large amounts of amphibole occurred in the samples, which shows that the original magma was water-rich [84], because amphibole and other water-bearing minerals crystallize only when water is saturated [85]. On the plots of Th/Yb vs. Ba/La and Th/Nb vs. Ba/Th diagrams (Figure 9c,d), there were constant Th/Yb and Th/Nb ratios and variable Ba/La and Ba/Th ratios, indicating a fluid-related enrichment. Thus, we propose that the magma was generated by the partial melting of a depleted mantle wedge that was metasomatized by subducting slab fluids.
Whole-rock REEs concentrations are mainly controlled by mantle composition and partial melting. Thus, the abundance and ratio of REEs can be widely used to define the characteristics of source area of mantle-derived rocks and the degree of mantle melting [86]. The Yb concentration in the initial melt during the melting of mantle peridotite was mainly controlled by residual garnet [87]. The melt formed by partial melting of mantle peridotite, accompanied by garnet residue, had a low Yb concentration and high LREE (such as La and Sm)/Yb ratios. However, the partial melting of spinel lherzolite will form a relatively flat melting trend, due to the fact distribution coefficients of La, Sm, and Yb in spinel are consistent [88]. A plot of Sm/Yb vs. Sm (Figure 10) indicates that the magmas were generated by moderate degree partial melting (20%–30%) of a garnet lherzolite source.
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Figure 8. Harker diagrams of the high-Mg diorite.
Figure 8. Harker diagrams of the high-Mg diorite.
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Figure 9. (a) Sr/Y vs. Y diagram and (b) (La/Yb)N vs. YbN diagram (modified after Kamei et al. [2]); (c) Th/Yb vs. Ba/La diagram (modified after Yang et al. [89]); (d) Th/Nb vs. Ba/Th diagram (modified after Hanyu et al. [90]).
Figure 9. (a) Sr/Y vs. Y diagram and (b) (La/Yb)N vs. YbN diagram (modified after Kamei et al. [2]); (c) Th/Yb vs. Ba/La diagram (modified after Yang et al. [89]); (d) Th/Nb vs. Ba/Th diagram (modified after Hanyu et al. [90]).
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Figure 10. Sm/Yb vs. Sm diagram of the high-Mg diorite (modified after Feng et al. [86]).
Figure 10. Sm/Yb vs. Sm diagram of the high-Mg diorite (modified after Feng et al. [86]).
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5.3. Tectonic Implications

The Hongtaiping high-Mg diorite samples have similar Nb concentrations (2.29–2.64 ppm) to island-arc basalt (generally <2 ppm) [91], with enrichment in LILEs and LREEs, and depletion of HFSEs and HREEs, showing affinities of arc-type magmatism. On the plots of La/Yb vs. Sc/Ni and Th/Yb vs. Ta/Yb diagrams (Figure 11), the samples were mainly near the region of the continental arc, which reflects their arc-related nature. Geochemical features of Permian–Middle Triassic magmatic rocks in the Yanbian area reflect that they formed under the subduction of the Paleo-Asian oceanic plate [14,18,25,26,34]. Parental magmas of Wangqing diorites (263 Ma) were likely derived from the mantle wedge, metasomatized by sediment melt and fluid from the subducting Paleo-Asian oceanic plate [35]. Syn-collisional monzogranites (249–245 Ma) [14] represent the Early Triassic collision of the CAOB with the NCC and the final closure of the Paleo-Asian Ocean, which is also supported by an early Triassic bimodal igneous rock association in the Helong and Longjing areas (259–251 Ma) [50] and the middle Triassic high-Mg diorites in the Hunchun area (241–240 Ma) [26]. Thus, we propose that the Middle Permian Hongtaiping high-Mg diorite formed in the subducting environment of the Paleo-Asian oceanic plate.
In central Jilin, a large amount of research has indicated that the Paleo-Asian Ocean had not been closed before the early Triassic. Wu et al. [92] reported that the piemontite-bearing chert in the Paleozoic strata at Yantongshan formed in a continental-margin environment and probably marked the final closure in the terminal Paleozoic to initial Mesozoic. Seluohe high-Mg andesite (252 Ma) derived from the partial melting of the enriched mantle wedge induced by hydrous fluid from subducted sediments in a subduction zone [93]. Combined with the volcanic rock in the Daheshen Formation, Cao et al. [18] and Yu et al. [94] suggested that the rhyolite-dacite-tracydacite suite reflect an active continental margin setting. Volcanic rocks with an age of 256 to 253 Ma in the Daheishan horst imply that they may be related to the volcanic arcs formed by the subduction of the Paleo-Asian oceanic plate [95]. Rb–Sr mineral isochron data indicate that the metamorphism age of the Hulan Group, intruded by the syn-collisional Dayushan pluton (248 Ma) [15], occurred at ~250 Ma, reflecting that the final oceanic closure took place in the Late Permian to early Triassic [43].
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Figure 11. (a) La/Yb vs. Sc/Ni diagram (modified from [96]); (b) Th/Yb vs. Ta/Yb diagram (modified from [97]).
Figure 11. (a) La/Yb vs. Sc/Ni diagram (modified from [96]); (b) Th/Yb vs. Ta/Yb diagram (modified from [97]).
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In the last decade, substantial data have supported the hypothesis that the Solonker–Xar Moron–Changchun–Yanji Suture (SXCYS) marks where the Paleo-Asian Ocean finally closed. A double-sided subduction model along the SXCYS has been established thanks to the following evidence: (1) the Late Permian–Middle Triassic high-Mg diorite or andesite are distributed along the SXCYS in both the southern combined NE China Blocks [26,98] and the northern NCC [93,99]; (2) igneous rock with arc affinities exists on both sides of the SXCYS [14,15,17,18,28,29,30,33,34,35,69,94,95,100]; (3) accretionary complexes related to subduction have been discovered in both the southern combined NE China Blocks and the northern NCC [25,93,99]. Liu et al. [19] gave a detailed discussion about the position of the eastern SXCYS and concluded that Changchun–Jilin–Dunhua–Yanji was the eastern extension of the SXCYS, as supported by paleontology, paleogeography, sediments and granitoid studies ([19] and references therein). As for the subduction polarity of the Hongtaiping high-Mg diorite, we propose that they formed under the northward subduction of the Paleo-Asian oceanic plate during the Middle Permian (Figure 12).
Minerals 12 01002 g012 550
Figure 12. Simplified cartoon model that shows the Middle Permian–Early Triassic igneous rocks in the Yanbian area and the northern margin of the NCC (modified from [100]).
Figure 12. Simplified cartoon model that shows the Middle Permian–Early Triassic igneous rocks in the Yanbian area and the northern margin of the NCC (modified from [100]).
Minerals 12 01002 g012

6. Conclusions

(1)
New LA–ICP–MS zircon U–Pb dating results show that the high-Mg diorite was ca. 267 Ma.
(2)
These rocks are calc-alkaline in nature, enriched in LREEs and LILEs, depleted in HREEs and HFSEs, and classified as sanukite.
(3)
The primary magma of the high-Mg diorite was derived from partial melting of the depleted mantle wedge that had been metasomatized by subduction-related fluids, with insignificant crystallization fractionation.
(4)
The magma was generated by moderate partial melting (20%–30%) of a garnet lherzolite source.
(5)
The high-Mg diorite was formed by the northward subduction of the Paleo-Asian oceanic plate during the Middle Permian.

Author Contributions

Conceptualization, S.L. and Y.R.; formal analysis, S.L. and Q.Y.; investigation, S.L., Y.R., Q.Y., Y.H. and X.Z.; writing—original draft, S.L.; supervision, Y.R.; writing—review and editing, Y.R.; funding acquisition, Y.R. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the National Natural Science Foundation of China (NSFC), Grant/Award Number: 41772062.

Data Availability Statement

All data generated or used in the study are contained in the submitted article.

Acknowledgments

We are grateful to editors and reviewers for their constructive comments and significant help in improving the document and to the personnel assisting in field campaigns and laboratories.

Conflicts of Interest

The authors declare no conflict of interest.

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Minerals 12 01002 g002 550
Figure 2. (a) High-Mg diorite; (b) high-Mg diorite (plane polar); (c) high-Mg diorite (crossed polar).
Figure 2. (a) High-Mg diorite; (b) high-Mg diorite (plane polar); (c) high-Mg diorite (crossed polar).
Minerals 12 01002 g002
Minerals 12 01002 g003 550
Figure 3. Representative zircon CL images of the high-Mg diorite. Red circles represent the analytical spots of LA–ICP–MS U–Pb analyses, and blue circles represent the analytical spots of Lu–Hf analyses. The U–Pb and Lu–Hf analytical diameters are 32 μm.
Figure 3. Representative zircon CL images of the high-Mg diorite. Red circles represent the analytical spots of LA–ICP–MS U–Pb analyses, and blue circles represent the analytical spots of Lu–Hf analyses. The U–Pb and Lu–Hf analytical diameters are 32 μm.
Minerals 12 01002 g003
Minerals 12 01002 g004 550
Figure 4. LA–ICP–MS zircon U–Pb diagrams of the high-Mg diorite. (a) Diagram of the concordia age; (b) Diagram of the weighted mean age.
Figure 4. LA–ICP–MS zircon U–Pb diagrams of the high-Mg diorite. (a) Diagram of the concordia age; (b) Diagram of the weighted mean age.
Minerals 12 01002 g004
Table
Table 2. LA–ICP–MS zircon U–Pb dating results of the high-Mg diorite.
Table 2. LA–ICP–MS zircon U–Pb dating results of the high-Mg diorite.
Sample No.Th (ppm)U (ppm)Th/UIsotopic Ratios Ages (Ma)
207Pb/206Pb207Pb/235U206Pb/238URho207Pb/206Pb207Pb/235U206Pb/238UD%
Ratio1σRatio1σRatio1σAges1σAges1σAges1σ
9150025.4373.440.350.072980.002031.805520.05030.179490.00247 1013.555.321047.518.211064.213.51
17HTP-6-1731.41490.781.490.053210.001460.303230.008380.041340.000540.303383926972613−23.2
17HTP-6-2247.62339.20.730.052610.001840.305770.010610.042160.000590.313125327182664−15
17HTP-6-3588.6433.11.360.05360.00160.306640.009150.04150.000550.313544327272623−26.6
17HTP-6-4963.011048.820.920.052410.001120.304450.006680.042140.000530.303032827052663−12.6
17HTP-6-5121.86166.110.730.052250.002610.308560.01520.042840.000680.3129683273122704−9
9150025.0472.540.350.077110.001851.902250.046050.178950.00238 1124.146.981081.916.111061.213.02
17HTP-6-7584.77466.381.250.051460.003230.297090.018320.041880.000760.302611082641426451.1
17HTP-6-8376.44438.10.860.0530.001660.314930.009830.04310.000580.313294627882724−17.6
17HTP-6-9709.47978.60.720.054590.000870.487710.008230.06480.000780.4939518403640552.4
17HTP-6-10216.3460.320.470.052830.002170.300470.012230.041260.000610.3032265267102614−19.3
9150025.2873.510.340.074090.001781.831550.044570.179320.00238 1043.847.741056.815.981063.213.03
17HTP-6-12155.87278.20.560.051270.002120.309590.012660.043790.000650.31253672741027649.4
17HTP-6-14255.06234.781.090.052760.002180.305960.012530.042060.000620.3131866271102664−17
17HTP-6-15223.78234.20.960.052160.001820.31090.010790.043230.00060.312925427582734−6.8
9150026.5076.280.350.074770.002121.844620.052330.178910.00251 1062.455.921061.518.68106113.72
17HTP-6-16155.47314.830.490.052570.001770.309280.01040.042660.000590.313105127482694−13.5
17HTP-6-17812.691143.950.710.054090.001950.373630.01340.050090.000710.3737555322103154−16.3
17HTP-6-18256.49316.650.810.052260.001490.304540.008740.042260.000560.302974127072673−10.3
17HTP-6-20314.09291.061.080.052110.00150.312060.0090.043430.000580.312904227672744−5.7
9150024.5671.580.340.074770.001871.849030.04680.179320.00242 1062.349.561063.116.681063.313.24
Table
Table 3. Whole-rock major (wt.%) and trace (ppm) element compositions of the high-Mg diorite.
Table 3. Whole-rock major (wt.%) and trace (ppm) element compositions of the high-Mg diorite.
Sample17HTP-6-117HTP-6-217HTP-6-317HTP-6-417HTP-6-5OU-6GBPG-1
Major elements (wt.%)
SiO243.9645.1946.5745.1345.62
Al2O313.3413.5714.7213.4213.78
Fe2O3t11.3711.0210.0511.0710.65
MgO16.5816.0313.3015.6815.08
CaO6.296.096.476.286.12
Na2O1.371.532.311.711.80
K2O0.430.480.910.500.61
MnO0.250.220.190.170.22
P2O50.230.220.250.220.23
TiO20.950.901.040.960.95
LOI5.144.934.044.784.76
Total99.90100.1999.8499.9299.81
Trace elements (ppm)
Li99.791.277.280.986.995.220.1
Be0.850.831.030.840.872.720.82
Sc18.717.820.718.718.522.215.4
V18918321119919312798.1
Cr132611869161226109571.8179
Co63.459.553.361.856.229.421.0
Ni56250635148646438.057.0
Cu10.511.713.315.811.345.027.4
Zn13811510510211010783.7
Ga17.816.718.417.117.123.819.4
As33521916682.121013.01.26
Rb18.717.744.821.523.912460.9
Sr366402542391459139360
Y11.911.713.712.712.328.519.1
Zr70.971.379.871.173.8174235
Nb2.292.292.642.322.4114.710.1
Mo0.480.401.201.030.480.531.75
Ag0.060.090.140.100.060.220.19
Cd0.070.070.100.090.060.10.09
Sn0.800.600.750.690.742.570.58
Sb4.263.732.882.923.630.530.06
Cs2.782.195.033.142.667.680.31
Ba66.177.818288.3106495894
La9.839.5211.69.5710.332.048.6
Ce22.722.026.122.323.270.591.2
Pr2.662.593.032.672.727.9111.1
Nd12.111.913.912.312.530.541.1
Sm2.662.572.992.702.675.976.39
Eu0.920.911.110.930.941.411.85
Gd2.442.382.812.552.525.274.69
Tb0.340.330.390.360.350.810.59
Dy1.981.932.262.102.024.933.08
Ho0.390.380.440.410.401.010.65
Er1.041.011.181.071.062.861.95
Tm0.140.140.160.150.140.430.29
Yb0.910.891.030.950.932.891.96
Lu0.140.130.150.140.140.440.30
Hf1.711.641.921.711.754.735.80
Ta0.130.130.150.130.141.040.40
W0.230.950.330.150.211.110.16
Tl0.160.130.320.170.170.520.28
Pb2.532.454.183.022.0529.313.9
Bi0.090.060.060.060.050.270.01
Th0.580.580.680.570.6411.511.5
U0.580.410.350.390.421.970.89
Table
Table 4. In situ zircon Hf isotopic compositions of the high-Mg diorite.
Table 4. In situ zircon Hf isotopic compositions of the high-Mg diorite.
Sample176Yb/177Hf2σ176Lu/177Hf2σ176Hf/177Hf2σHfiεHf(0)εHf(t)TDM (Ma)T2DM (Ma)fLu/Hft(Ma)
17HTP-6-10.0371240.0004780.0015740.0000220.2829070.0000170.2829004.810.3496630−0.95261
17HTP-6-20.0410570.0004200.0017140.0000150.2828930.0000350.2828844.39.8519663−0.95266
17HTP-6-30.0902210.0004060.0031960.0000240.2828130.0000230.2827981.56.7660860−0.90262
17HTP-6-40.1245370.0014270.0047110.0000260.2828510.0000230.2828272.87.9631788−0.86270
17HTP-6-50.0271300.0006500.0009960.0000230.2828750.0000140.2828703.69.3535696−0.97264
17HTP-6-60.0240010.0008500.0008550.0000310.2828440.0000170.2828402.58.4576759−0.97272
17HTP-6-70.1106440.0015350.0040200.0000400.2828780.0000200.2828583.78.8577724−0.88261
17HTP-6-80.0287200.0004450.0010580.0000190.2828660.0000170.2828613.39.2547708−0.97276
17HTP-6-90.1440280.0008860.0049360.0000150.2828690.0000220.2828453.48.4606751−0.85266
17HTP-6-100.0710300.0006550.0026670.0000330.2829120.0000220.2828984.910.5505627−0.92273
17HTP-6-110.0355740.0008400.0012890.0000330.2829570.0000160.2829506.512.2422511−0.96269
17HTP-6-120.0839500.0016690.0030280.0000540.2828730.0000180.2828583.68.9568722−0.91267
17HTP-6-130.0495840.0003550.0018580.0000150.2827730.0000180.2827640.05.7695929−0.94274
GJ-1-10.0068310.0000100.0002950.0000000.2820150.000021
GJ-1-20.0068550.0000130.0002960.0000000.2819710.000019
GJ-1-30.0068490.0000080.0002960.0000000.2820060.000020
GJ-1-40.0067850.0000130.0002960.0000000.2820150.000022
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Lu, S.; Ren, Y.; Yang, Q.; Hao, Y.; Zhao, X. Petrogenesis and Tectonic Implication of the Hongtaiping High-Mg Diorite in the Wangqing Area, NE China: Constraints from Geochronology, Geochemistry and Hf Isotopes. Minerals 2022, 12, 1002. https://doi.org/10.3390/min12081002

AMA Style

Lu S, Ren Y, Yang Q, Hao Y, Zhao X. Petrogenesis and Tectonic Implication of the Hongtaiping High-Mg Diorite in the Wangqing Area, NE China: Constraints from Geochronology, Geochemistry and Hf Isotopes. Minerals. 2022; 12(8):1002. https://doi.org/10.3390/min12081002

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Lu, Siyu, Yunsheng Ren, Qun Yang, Yujie Hao, and Xuan Zhao. 2022. "Petrogenesis and Tectonic Implication of the Hongtaiping High-Mg Diorite in the Wangqing Area, NE China: Constraints from Geochronology, Geochemistry and Hf Isotopes" Minerals 12, no. 8: 1002. https://doi.org/10.3390/min12081002

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